Fresh and Brackish Water Ostracods of Upper MioceneDeposits, Arguvan/Malatya (Eastern Anatolia)

AT‹KE NAZ‹K1,2, ‹BRAH‹M TÜRKMEN3, CAL‹BE KOÇ3, ERCAN AKSOY3, N‹YAZ‹ AVfiAR2 & HÜLYA YAYIK2

1 Ad›yaman University, Vocational Education Faculty, TR–02040 Ad›yaman, Turkey(E-mail: anazik@cu.edu.tr)

2 Çukurova University, Department of Geological Engineering, TR–01330 Adana, Turkey3 F›rat University, Department of Geological Engineering, TR–23119 Elaz›¤, Turkey

Abstract: The Neogene Alibonca, Küseyin, Parçikan, Boyaca formations and the Mamaar volcanic unit occur atArguvan (Malatya, Eastern Anatolia). Nine species of ostracods were identified and assigned to four genera insamples collected from the Küseyin and Parçikan formations. The faunal content in these units was characterizedby few ostracod species and abundant individuals. Most samples contained fewer than nine species. Ilyocyprisbradyi, Ilyocypris gibba, Candona parallela pannonica and Heterocypris salina are described in the KüseyinFormation. Cyprideis pannonica, Cyprideis anatolica, Cyprideis torosa, Ilyocypris gibba, Candona angulata, Candonaneglecta, Candona parallela pannonica and Heterocypris salina are described in Parçikan Formation. Cyprideis,which has ecophenotypic ornamentations (smooth, punctuated, reticulated or nodes), is the dominant genus in theParçikan Formation.

Lithological features and fossil contents of the Upper Miocene units suggest that the Küseyin Formation wasdeposited by a meandering river and the Parçikan Formation was formed in a shallow lacustrine environmentassociated with swamps.

The ostracod assemblages have been correlated with ostracod species of the Tethys and Paratethys regions.Cyprideis pannonica is observed in the Paratethys and Tethys bioprovinces. Cyprideis torosa, Ilyocypris gibba,Ilyocypris bradyi, Heterocypris salina, Candona angulata, Candona neglecta Sars are known in Europe and theTethys bioprovince.

Key Words: Neogene, Eastern Anatolia, Ostracoda, freshwater, brackish water

Üst Miyosen Çökellerinin Tatl› ve Ac›su Ostrakodlar›, Arguvan/Malatya (Do¤u Anadolu)

Özet: Arguvan (Malatya, Do¤u Anadolu) yöresinde Neojen birimleri Alibonca, Küseyin, Parçikan, Boyacaformasyonları ve Mamaar volkanik birimi ile temsil edilmektedir. Küseyin ve Parçikan formasyonlarından derlenenörneklerde ostrakodlardan dört cinse ait dokuz tür saptanmıfltır. Bu birimlerin fauna içeri¤ini fert sayısı bol, türsayısı az ostrakodlar oluflturmaktadır. Örneklerin ço¤unda dokuz ostrakod türü daha az sayıda temsil edilmektedir.Ilyocypris bradyi, Ilyocypris gibba, Candona parallela pannonica and Heterocypris salina Küseyin Formasyonu’nda,Cyprideis pannonica, Cyprideis anatolica, Cyprideis torosa, Ilyocypris gibba, Candona angulata, Candona neglecta,Candona parallela pannonica and Heterocypris salina ise Parçikan Formasyonu’nda tanımlanmıfltır. Ekofenotipiksüslere (düz, noktalı, retiküllü ve nodlu) sahip Cyprideis’ler, Parçikan Formasyonu’nda baskın cins olarakgözlenmifltir.

Üst Miyosen birimlerinin litolojik özellikleri ve fosil içeriklerine göre, Küseyin Formasyonu menderesli akarsuortamında, Parçikan Formasyonu ise bataklıkla iliflkili sı¤ göl ortamında depolanmıfltır.

Ostrakod toplulu¤u, Tetis ve Paratetis ostrakodları ile karflılafltırılmıfltır. ‹nceleme alanında, Paratetis ve Tetisbioprovenslerinde bilinen Cyprideis pannonica, Avrupa’da ve Tetis bioprovensinde bilinen ostrakodlardan Cyprideistorosa, Ilyocypris gibba, Ilyocypris bradyi, Heterocypris salina, Candona angulata, Candona neglecta’ın varlı¤ıbelirlenmifltir.

Turkish Journal of Earth Sciences (Turkish J. Earth Sci.), Vol. 17, 2008, pp. 481–495. Copyright ©TÜB‹TAKFirst published online 04 February 2008

481

Introduction

Large Neogene basins formed in continental areas in theEastern Mediterranean region (Figure 1). In EasternAnatolia Neogene rocks are mainly characterized by

fluvial and fluvio-lacustrine sediments alternating withseveral coal layers and associated with volcanic-volcaniclastic rocks. In addition, fresh to brackish watersystems are widely distributed in Anatolia including the

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study area, located in the southern part of Arguvan(Malatya) in Eastern Anatolia (Figure 2). Several papersdescribe studies of fresh and brackish water ostracodsfrom the Neogene of Turkey (Bassiouni 1979; Gökçen1979a, b; Freels 1980; fiafak et al. 1992; Nazik et al.1992, 2005; Tuno¤lu 1984; Tuno¤lu & Çelik 1995;Tuno¤lu et al. 1995; Tuno¤lu & Gökçen 1985, 1997;Ünal & Tuno¤lu 1996; Tuno¤lu & Ünal 2001a, b; Atay &Tuno¤lu 2002; Witt 2003; Matzke-Karasz & Witt 2005).Detailed geological, petrographical, sedimentologicalresearch in this region has also been conducted (fiaro¤lu& Güner 1981; fiaro¤lu & Yılmaz 1984, 1986; Türkmen& Aksoy 1998; Ercan & Asutay 1993; Kürüm 1994;Alparslan & Terzio¤lu 1996; Kürüm & Bingöl 1996;Sönmez 2004; Türkmen et al. 1998, 2004).

This paper aims to define fresh and brackish waterostracods from the Neogene in the Arguvan (Malatya)area in Eastern Anatolia and to correlate them with thosein other Neogene basins in Turkey and Europe.

Material and Methods

In this investigation, 150 clastic samples were collectedfrom three measured stratigraphic section. 100 grams ofdry sediment was immersed in a 20% H2O2 (HydrogenPeroxide) water solution, washed and passed through a125 μm sieve and fossils were picked from the residue.Gastropods, gyrogonites and plant debris were foundtogether with a well preserved ostracod fauna, found inthe Küseyin and Parçikan formations.

Photographs were taken with a SEM (Jeol JSM-6400). The fossil material is housed in the Department ofGeology, Faculty of Engineering & Architecture,Çukurova University in Adana, Turkey.

Geological Setting

The Neogene units in eastern Anatolia are represented byshallow marine, fluvial, and lacustrine sediments, coalseams and volcanic rocks, belonging to the Alibonca,Malatya volcanics, and the Küseyin, Parçikan and Boyacaformations (Figure 3). This sequence overlies thePermo–Triassic Keban metamorphic units.

The Alibonca Formation

This formation is characterized by reef core, reef frontand lagoonal deposits including abundant Late

Oligocene–Early Miocene benthic foraminifera around theMalatya area (Türkmen et al. 2004). The KüseyinFormation lies unconformably on the upper part of thisunit outside the study area.

The Malatya Volcanics

This unit, named by Ercan & Asutay (1993), is composedof basalt and andesite in northern Arguvan and Arapgir.Its Early to Middle Miocene age has been established byradiometric data and its stratigraphic position (Türkmenet al. 2004).

The Küseyin Formation

This formation was defined by Önal (1995a, b). Its type-location is in Küseyin Village. Its sedimentolical featureswere studied by Türkmen et al. (2004, 2007). It iscomposed of red mudstone, overlain in turn byconglomerate and sandstone, and ís probably LateMiocene in age, according to stratigraphical relationshipand ostracods (Türkmen et al. 2004). It is overlain by theParçikan Formation in the study area.

The Parçikan Formation

It was named by Önal (1995a, b) and its sedimentologicalfeatures were studied by Türkmen et al. (2004, 2007).The type-locality or location is close to Parçikan Village.This formation consists of fine, medium-grainedsandstone, siltstone, organic-rich, grey-green claystone,marl, coal and clayey limestone levels (Figure 3).Ostracods, gastropods, gyrogonits and plant debris areabundant. Lignite deposits occur in both the lower andupper levels of the Parçikan Formation, which is LateMiocene in age, based on spore and pollen data (Türkmenet al. 2004) and ostracod assemblages. The ParçikanFormation is overlain by the Boyaca Formation.

The Boyaca Formation

This formation was described by Önal (1995a, b) andexamined by (Türkmen et al. 2004, 2007). The type-locality is in Boyaca Village, within the study area. TheBoyaca Formation is composed of reddish mudstone, siltymudstone, conglomerate and sandstone, deposited in alow-sinuosity river environment. Its Late Miocene age isbased on its relationship with the underlying ParçikanFormation (Türkmen et al. 2004).

A. NAZ‹K ET AL.

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LATE MIOCENE OSTRACODS

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Parçikan FormationAlibonca Formation(U. Oligocene-L. Miocene)

Boyaca Formation

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Figure 2. Simplified geological map of the study area (Türkmen et al. 2004), showing the locations of the sections inthis study.

Climatic and Tectonic Evolution in the Miocene ofEastern Anatolia

Miocene floral data indicate that climate in Turkey waswarm subtropical in the Early Miocene, subtropical in theMiddle Miocene and temperate in the Late Miocene(Akgün & Akyol 1992; Kayseri & Akgün 2006). The

warm climatic conditions determined with thequantitative climatic values during the Late Miocene inAnatolia are defined by the widespread presence of Ilex,Fagacea and Corylus in Central Anatolia (Kayseri & Akgün2006). In the Malatya Basin, the dominance of pollenfrom Pinus, Quercus, Castanea, Cyrillaceae and Ulmus, as

A. NAZ‹K ET AL.

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LATE MIOCENE OSTRACODS

486

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well as the presence of subtropical plant taxa, such asAlnus, Carya, and Engelhardia, suggest a subtropical(moist and hot) palaeoclimate in the Late Miocene(Türkmen et al. 2007).

The Tertiary marine regression was related toregional uplift following the closure of Neotethys andregional continent-continent collision in the MiddleMiocene, marking the beginning of the Neotectonicperiod (fiengör 1980; fiengör & Yılmaz 1983; Jackson &McKenzie 1984; Dewey et al. 1986; Hempton 1987).Both strike-slip and extensional regimes alternated andcoexisted in the Neogene period and, gave rise to anumber of fault-controlled basins in Eastern Anatolia.Tectonic evolution during the Early Neogene in EasternTurkey was largely controlled by the convergent andcolliding Arabian and Anatolian plates. ENE–WSW-directed folds and thrust faults developed related to aNNW–SSE compressional regime. During theOligocene–Early Miocene, shallow-marine carbonate andclastics were deposited in Eastern Turkey. Fluvial andlacustrine deposits accompanied by Middle Miocenevolcanism filled E–W-trending intramontane basins,related to N–S extension (Aksoy et al. 1996, 2005).Alluvial and lacustrine facies associations mostlydeveloped in the fault-bounded basin in Eastern Anatolia.

Thick alluvial and lacustrine facies were depositedduring the Late Miocene in the Malatya Basin, in EasternTurkey, which is an NE–SW-oriented graben, developedin an extensional setting in the Middle to Late Miocene.Facies distributions in such basins are mainly controlledby tectonics, climate, hinterland characteristics, baselevel-changes and sediment supply (Nichols & Watchorn1998; Bohacs et al. 2000; Nichols & Uttamo 2005).

Similar architectural styles observed in the alluvial andlacustrine units were interpreted as a tectonic signaturelikely to characterize high-accommodation basins thatsubsided rapidly along the basin bounding faults (Davies& Gibling 2003). The Malatya basin-fill characteristicsand the regional tectonics indicate that the alluvial andlacustrine facies associations were developed in responseto regional extension related to strike-slip movement ofthe Malatya Fault Zone in a subtropical climate.

Non-marine Ostracod Faunas of theArguvan/Malatya (Eastern Anatolia) and TheirCorrelations With Other Neogene Basins of Tethysand Paratethys

Published data by Van Morkhoven (1963), Krstic (1968),Kilenyi (1972), Hartmann & Puri (1974), Bassiouni(1979), Gökçen (1979a), Freels (1980), Nazik et al.(1992), fiafak et al. (1992), Tuno¤lu & Çelik (1995),fiafak (1997a, b), van Harten (2000), Tuno¤lu & Ünal(2001a), Witt (2003), Atay & Tuno¤lu (2004), Keyser(2005) were used for identification of ostracod taxa. Ninespecies belonging to four genera were described from150 rock samples. A low diversity fauna was recorded inthe Parçikan and Küseyin sections in which Cyprideis isthe dominant genus. The ostracod assemblage issupposed to be in situ due to the presence both of wellpreserved juvenile specimens and adult carapaces.

Ilyocypris bradyi (Sars), Ilyocypris gibba (Ramdohr),Candona parallela pannonica (Zalanyi) and Heterocyprissalina (Brady) are found in the two of nine samplescollected from the Küseyin Formation. Cyprideispannonica (Mehes), Cyprideis anatolica Bassiouni,Cyprideis torosa (Jones), Ilyocypris gibba (Ramdohr),Candona angulata Mueller, Candona neglecta Sars,Candona parallela pannonica (Zalanyi) and Heterocyprissalina (Brady), characean gyrogonites and gastropodshells were identified in the Parçikan Formation (Figures4 & 5, Plate I).

C. pannonica, C. anatolica and Cyprideis torosa wereconsistently common throughout the Parçikan section. H.salina was present at 8 m, between 21 to 25 m and 64m in the claystone level of the Parçikan section. Candonaspecies were found between 21 to 34 m of the Parçikansection (Figure 4). H. salina, I. bradyi, I. gibba and C.parallela pannonica were determined in the marl andclaystone levels of the Küseyin Section. The smooth andnoded C. torosa specimens were found together withHeterocypris, Ilyocypris and Candona at different levels ofParçikan Section.

Bassiouni (1979), Gökçen (1979a, b, 1982), Freels(1980), Tuno¤lu (1984), Tuno¤lu & Çelik (1995),Tuno¤lu et al. (1995), Tuno¤lu & Gökçen (1985, 1997),fiafak et al. (1992), Nazik et al. (1992), Tuno¤lu & Ünal

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(2001a, b), Atay & Tuno¤lu (2002), Witt (2003),Matzke-Karasz & Witt (2005) studied fresh and brackishwater ostracods from the Neogene of Turkey. Bassiouni(1979) investigated brackish and marine ostracods fromthe Neogene in different areas of Turkey, but, as he gaveonly general information about non-marine ostracods inthe Malatya area, non-marine ostracods of the Arguvandistrict (Malatya) were studied in this project.Biostratigraphic subdivision of the Late Miocene has notbeen established in the study area, but thechronostratigraphic approach was carried out usingostracod studies of Tethys and Paratethys andpalynological data. C. neglecta, C. torosa, I. bradyi, I.gibba, H. salina are recorded from the Miocene to theRecent.

The first appearance of Cyprideis was pointed out inthe Upper Volhynian in Eastern Paratethys, and theSarmatian in the Central Paratethys region (Carbonnel &Jiricek 1977; Jiricek 1983). The first Cyprideis level wasrecognized in Middle Tortonian brackish water deposits inCrete of the Eastern Mediterranean by Sissingh (1974).Also, C. pannonica was described in zone NO-15 and NO-16 (Lower Pannonian) of the Paratethys (Jiricek 1983;Jiricek & Riha 1991). In addition, this species was foundin the Upper Miocene of the Lago Mare environment inthe Eastern Mediterranean (Spezzaferri et al. 1998).Other occurences are recorded in the: (i) LowerPannonian of the Vienna Basin (Kollmann 1960), (Jiricek& Riha 1990), (ii) Upper Miocene of Italy (Decima 1962),(iii) Upper Miocene (Messinian) of the Mediterranean(Carbonnel 1978), (iv) Upper Miocene of Marmara,Southwest and Middle Anatolia, Turkey (Bassiouni 1979),(v) Pannonian–Pontian of the Bakırköy, ‹stanbul, Turkey(fiafak 1997b), and (vi) Pannonian–Pontian of theGelibolu Peninsula, Turkey (Ünal & Tuno¤lu 1996;Tuno¤lu & Ünal 2001a, b; Atay & Tuno¤lu 2002).

The first appearance of C. torosa was in the LateMiocene and its stratigraphical range is Miocene toRecent. Its general distribution is widespread throughoutthe brackish coastal waters of Europe, Western andCentral Asia, the Mediterranean region of North Africa,the Middle East and North America and lakes in theCentral Africa (van Harten 2000; Meisch 2000). The C.torosa Zone has been correlated with NP-20 of Blow(1969) in the Piacenzian and NO-14 of CentralParatethys in the Romanian by Jiricek (1983). A I-Cyprideis pannonica and Cyprideis torosa assemblage

Zone is described from the Early Pannonian in theGelibolu Peninsula (NW Turkey) by Tuno¤lu & Ünal(2001a). Other Neogene occurences are in the: (i)Messinian of Italy (Decima 1962); (ii) Neogene of theRhone Basin (Carbonnel 1969), (iii) Pliocene of variousareas of Turkey (Bassiouni 1979), (iv) Pliocene ofsouthern Aegean Islands (Sissingh 1974), (v)Pannonian–Pontian of Bakırköy, ‹stanbul, Turkey (fiafak1997b), (vi) Pannonian–Pontian of the GeliboluPeninsula, Turkey (Tuno¤lu & Ünal 2001a, b; Atay &Tuno¤lu 2002), and (vis) Pannonian to Pleistocene of NWAnatolia (Matzke-Karasz &Witt 2005) .

The Late Miocene to Recent H. salina is common in theslightly brackish waters along the coasts of the North andBaltic Seas (Meisch 2000). This species is found in theMiddle Miocene of Serbia (Krstic 1972), in the UpperMiocene of SW Anatolia (Freels 1980), in the UpperMiocene in Slovakia (Pipik 2001), in the UpperMiocene–Lower Pliocene of Western Anatolia (Witt2003), and in the Pannonian–Pleistocene of NW Anatolia(Matzke-Karasz &Witt 2005).

A fossil record of I. gibba is found in the UpperMiocene of France (Carbonnel 1969), in the LowerMiocene and Pliocene of Central Anatolia (Tuno¤lu &Çelik 1995; Tuno¤lu et al. 1995) and in the Pannonian ofSlovakia (Pipik 1998). Its general distribution is Europe,Africa, the Middle East, Central Asia, China, and bothNorth and South America (Meisch 2000).

I. bradyi ranges from Miocene to Recent (Meisch2000) and is distributed across Europe, North Africa, theMiddle East, central Asia, China and North America.

C. neglecta ranges from Upper Miocene to Recent. Itis found in the Upper Miocene of France (Carbonnel1969), in the Pliocene of the Eastern Taurides (fiafak etal. 1992) and Central Anatolia (Tuno¤lu et al. 1995). Itsgeneral distribution is across Europe, North Africa, Asia,and North America (Meisch 2000).

Meisch (2000) claimed that C. angulata ranges fromthe Lower Pleistocene to Recent, but it has also beenfound in the Upper Miocene in Bulgaria (Stancheva 1963,1990) as well as the Pliocene to Lower Pleistocene(Gurnet et al. 1976).

C. parallela pannonica is known from the UpperPannonian of Hungary (Zalanyi 1959), the Tortonian ofTrebon Basin (Kheil 1964) and the Pontian to Holoceneof Turkey (Gökçen 1979a, b; Nazik et al. 1992; fiafak et

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al. 1992, 1999; Tuno¤lu et al. 1997; Tuno¤lu & Ünal2001a, b).

C. anatolica was firstly described in the Pliocene ofTurkey by Bassiouni (1979). It has since been found inthe Upper Miocene–Pliocene sequence of the AntakyaBasin (fiafak 1993), Pannonian–Pontian of Bakırköy,‹stanbul (fiafak 1997b) and Upper Miocene of Hatay(Parlak et al. 1998) in Turkey, but remains only knownin Turkey.

Results

Ostracod faunas of the 150 samples from the Küseyinand the Parçikan formations have been studied and ninespecies were found. Ostracod assemblages have beensuccesfully applied to the interpretation of differentdepositional sequences. Size, shape and ornament ofindividual ostracod shell are important indicators ofpalaeoenvironmental condition (Boomer et al. 2003).Nodose Cyprideis occur at different levels of the ParçikanFormation. Modern Cyprideis torosa develop phenotypictubercles on one or both valves when moving to lesssaline environments (Van Morkhoven 1963; Keyser2005). These nodes of Cyprideis torosa only occur atwater salinities of about 2–5‰ (Boomer et al. 2003).Keyser (2005) stated that nodose ostracods can be usedas an environmental marker for low salinity and/or lowcalcium content. Bassiouni (1979) stated that ‘the rarityor the complete absence of the noded Cyprideismorphotype in the Upper Miocene may prove at leasttemporal dry climatic conditions which led to meso- topliohaline-water salinity’. Nodose ostracods reflect thatthere was a decrease in salinity and an increase in organicmatter in their environment (Rundic 2001). Cyprideistorosa tolerated a wide salinity range (1‰ to more than40‰), although the presence of Ilyocypris at some levelsof the studied formation suggests that salinities neverexceeded about 5‰ (oligohaline). I. gibba is found insmall and shallow permanent water bodies with clayey,fine-mudded or sandy substrate and I. bradyi lived in both

muddy and sandy substrates (Meisch 2000). C. neglectais reported from slightly salty inland and coastal waterswithin a salinity range of 0.5–16‰ (Meisch 2000) andgenerally with muddy substrates (Besonen 1997). C.angulata clearly prefers slightly salty waters (Meisch2000).

The Parçikan Formation has mainly clays and mudswith intercalations of silty and sandy material and ligniteseams. Gastropods were often abundant enough to formshelly beds. In conclusion, ostracod faunas of the ParçikanFormation and its lithological properties indicate mainlybrackish and occasionally fresh water conditions in thestudy area. Cyprideis torosa, Ilyocypris gibba, Ilyocyprisbradyi, Heterocypris salina, Candona angulata andCandona neglecta are the cosmoplitan species in Europeand Tethys bioprovince. As Cyprideis pannonica and C.parallela pannonica Paratethyan ostracod are found in theMalatya-Arguvan region of eastern Anatolia. Tethyan andParatethyan ostracods are found in the region.

Acknowledgements

This study was supported by Çukurova University,Academic Research Projects Unit Grant MMF2004-YL53and TÜB‹TAK (The Scientific and Technological ResearchCouncil of Turkey) Grant 102Y124. The first authorwould like to thank John Ryan (International Center forAgricultural Research in the Dry Areas -ICARDA, Aleppo,Syria), who carefully read the manuscript and made manyvery helpful comments. The authors would like to expresstheir thanks to Dr. Gross (Landesmuseum Joanneum,Austria), Cemal Tuno¤lu (Hacettepe University) and athird referee who wishes to remain anonymous for theirvaluable reviews and their input on improvements to themanuscript. The authors acknowledge Tuncay Akkoyunand M. Fatih Kaya for their support during the fieldstudies, and sincerely thank Feyza Dinçer (ÇukurovaUniversity) for fossil photographs. John A. Winchesteredited the English of the final text.

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Received 03 October 2007; revised typescript received 04 January 2008; accepted 29 January 2008

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Plate I. Ostracods of the Neogene in the study area.

1. Candona neglecta Sars, outside view of left valve, X50. 2–3. Candona angulata Mueller.2. Outside view of the right valve, X 45.3. Outside view of left valve, X 45, HBP-17, Parçikan Formation.4. Candona parallela pannonica (Zalanyi), outside view of right valve, X 80, HBP-17, Parçikan

Formation. 5–6. Cyprideis torosa (Jones), 5. Outside view of left valve, X 56, 6. Inside view of the right valve, X63,

HBP-25, Parçikan Formation.7. Cyprideis anatolica Bassiouni, outside view of right valve, X85, HBP-25, Parçikan Formation.8–9. Cyprideis pannonica (Mehes), 8. Outside view of left valve, X65, 9. Outside view of right valve,

X68, HBP-17, Parçikan Formation.10–11. Cyprideis torosa (Jones) with nodes, 10. Outside view of left valve, X85, 11. Dorsal view, X80,

HBP-25, Parçikan Formation.12. Ilyocypris gibba (Ramdohr), outside view of left valve, X83, HBP-32, Parçikan Formation.13. Ilyocypris bradyi (Sars), outside view of left valve, X83, HK-7, Küseyin Formation.14. Heterocypris salina (Brady), outside view of left valve, X80, HBP-17, Parçikan Formation.15. Characean gyrogonites, X35, HBP-42, Parçikan Formation. 16. Gastropoda, X20, HBP-16,

Parçikan Formation.

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14

8

32

10

56

11

1

4

12

97

1315

16